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Figure 1. Map showing Atlantic coast of the United
                                                                                           States with population density by county (U.S.
                                                                                           Census Bureau, 2010) placed alongside Late
                                                                                           Holocene and twentieth-century relative sea-level
                                                                                           rise (RSL) rise curves (2 � errors; Engelhart et al.,
                                                                                           2009). RSL rise predicted from glacio-hydro-isostatic
                                                                                           adjustment (GIA) modeling is from the M2 viscosity
                                                                                           model (Peltier, 1996). Yellow shaded region brackets
                                                                                           area of highest RSL rise on the Atlantic coast; dotted
                                                                                           white line indicates maximum extent of the
                                                                                           Laurentide ice sheet (LIS) (Dyke et al., 2002);
                                                                                           magenta lines indicate tracks of major recent storms.
                                                                                           PL, S, MP—Locations of coastal deposits dating to
                                                                                           MIS 3 near central Chesapeake Bay (67–37 ka, n = 8;
                                                                                           Pavich et al., 2006; Litwin et al., 2013), in southern
                                                                                           Virginia (50–33 ka, n = 2; Scott et al., 2010), and
                                                                                           North Carolina (59–28 ka, n = 15; Mallinson et al.,
                                                                                           2008, Parham et al., 2013), respectively. A–A´ shows
                                                                                           location of Figure 2A.

landforms above sea level (<8 m above mean sea level [asl]) near                           did not experience high-stand deposition after MIS 5 (e.g.,
central Chesapeake Bay (PL, Fig. 1), at the mouth of Chesapeake                            Ramsey, 2010). The presence of near-shore MIS 3 deposits near
Bay (S, Fig. 1), and on the North Carolina coast (MP, Fig. 1) indi-                        present sea level suggests an alternative sea-level history for the
cate estuarine deposition throughout MIS 3 (67–32 ka). Eustatic                            region, one that implies forebulge uplift of at least 40 m since the
sea level during this time was highly variable but always ~40–80 m                         time of deposition. This uplift has been attributed to growth of
lower than present (Fig. 2) (Siddall et al., 2008). These new data                         the last glacial maximum (LGM; MIS 2) forebulge (Pavich et al.,
challenge the long-held implication that locations within the                              2006; Mallinson et al., 2008; Scott et al., 2010; Parham et al., 2013)
Chesapeake Bay region, and specifically the Delmarva Peninsula,                            that remains uplifted out of isostatic equilibrium (Potter and
                                                                                           Lambeck, 2003).
                                                                                                                                                                   GSA TODAY | www.geosociety.org/gsatoday
                                                                                             This paper uses multiple methods to date deposits within the
                                                                                           zone of greatest subsidence in the Chesapeake Bay region (Fig. 1)
                                                                                           and place today’s rapid relative sea-level rise into the context of a
                                                                                           several-million-year geologic framework. We used a light detec-
                                                                                           tion and ranging (LiDAR) digital elevation model (DEM) to
                                                                                           analyze low-relief landforms and conducted extensive drilling to
                                                                                           constrain the Pleistocene stratigraphic framework. Our data show
                                                                                           that regional subsidence related to collapse of the MIS 6 glacio-
                                                                                           isostatic forebulge impacted the mid-Atlantic region well into
                                                                                           MIS 3, tens of thousands of years after MIS 5 deglaciation. Long-
                                                                                           lasting subsidence associated with collapse of the MIS 6 forebulge
                                                                                           suggests that present-day subsidence related to the collapse of
                                                                                           the MIS 2 forebulge will continue for the foreseeable future. We
                                                                                           conclude that ongoing subsidence adds to the impacts of sea-level
                                                                                           rise driven by warming climate and melting ice sheets and should
                                                                                           be considered in coastal sea-level risk assessments.

Figure 2. (A) Schematic cross section showing relationship of land surface to              STUDY SITE AND METHODS
relative sea level at specific times in glacial cycles as a function of distance from the
Laurentide ice sheet (LIS). Adapted by permission from D. Krantz and C. Hobbs                To reconstruct the sea-level history in Chesapeake Bay, we
(2014, pers. comm.). Location of A–A´ cross section is indicated in Figure 1.              focused on the Blackwater National Wildlife Refuge (~110 km2;
(B) Oxygen isotope and sea-level curves for the past 150 k.y. from Lisiecki and            red-bordered rectangle on Fig. 1), which experienced major inun-
Raymo (2005) and Thompson and Goldstein (2006), respectively. The                          dation and transformation of wetlands to open water in the twen-
glacioisostatic (land surface) curve (after Scott et al., 2010) is based on ages           tieth century (Fig. 3). Sediment from 70 boreholes was described,
produced for shoreline deposits in the mid-Atlantic region and illustrates how             analyzed, and sampled. The DEM (Fig. 4) was used to characterize
land-surface elevation change induced by glacio-hydro-isostatic adjustment can             the geomorphology. We constrained the oldest erosional event
account for submergence of the Chesapeake Bay region when eustatic sea level was           preserved directly above the underlying Miocene strata using
much lower than present. VPDB—Vienna Pee Dee Belemnite.                                    cosmogenic nuclide isochron burial dating (Balco and Rovey,
                                                                                           2008). We dated 28 samples using optically stimulated lumines-
                                                                                           cence (OSL) dating. The OSL ages allow us to develop a

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